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Sedimentary and Foraminiferal Evidence of the 2011 Tōhoku-Oki Tsunami on the Sendai Coastal Plain, Japan

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Sedimentary and Foraminiferal Evidence of the 2011 Tōhoku-Oki Tsunami on the Sendai Coastal Plain, Japan Sedimentary Geology 282 (2012) 78–89 Contents lists available at SciVerse ScienceDirect Sedimentary Geology journal homepage: www.elsevier.com/locate/sedgeo Sedimentary and foraminiferal evidence of the 2011 Tōhoku-oki tsunami on the Sendai coastal plain, Japan Jessica E. Pilarczyk a,b,⁎, Benjamin P. Horton a, Robert C. Witter c, Christopher H. Vane d, Catherine Chagué-Goff b,e, James Goff b a Sea Level Research, Department of Earth and Environmental Science, University of Pennsylvania, 240 S. 33rd Street, Philadelphia, PA 19104‐6316, USA b Australia-Pacific Tsunami Research Centre, School of Biological, Earth and Environmental Sciences, University of New South Wales, Sydney 2052, Australia c United States Geological Survey/Alaska Science Center, Anchorage, AK 99508, USA d British Geological Survey, Keyworth, Nottingham NG92BY, UK e Australian Nuclear Science and Technology Organisation, Locked Bag 2001, Kirrawee DC, NSW 2232, Australia article info abstract Article history: The 2011 Tōhoku-oki megathrust earthquake (Mw 9.0) generated a tsunami that reached the Sendai coastal Received 16 March 2012 plain with flow heights of ~2 to 11 m above TP (Tokyo Peil). We examined the tsunami deposit exposed in 14 Received in revised form 23 August 2012 shallow trenches along a ~4.5‐km transect perpendicular to the coast. We primarily document the strati- Accepted 27 August 2012 graphical, sedimentological, foraminiferal and geochemical characteristics of the Tōhoku-oki tsunami deposit Available online 7 September 2012 and perform a preliminary comparison with sediments deposited by the Jōgan tsunami of A.D. 869. In the coastal forest and rice fields inundated by the Tōhoku-oki tsunami, a poorly sorted, dark brown soil is Keywords: Sendai Plain buried by a poorly sorted, brown, medium-grained sand deposit. In some trenches located more than 1.2 km 2011 Tohoku-oki tsunami inland, the sand is capped by a thin muddy-sand layer. The tsunami deposit, although highly variable in Jogan tsunami thickness, is generally thickest (25 cm) near the coastal dune and thins to less than 5 mm at ~4.5 km inland. Foraminifera The tsunami deposit was discriminated from the underlying soil by the appearance of recent and fossil fora- minifera and a pronounced increase in grain size that fined upward and landward. The recent foraminifera preserved in the sandy facies of the deposit are rare and showed evidence of prolonged subaerial exposure (e.g. pitting, corrosion, fragmentation). Recent foraminifera likely originated from coastal dune and beach sediments that were breached by the tsunami. Calcified and sediment in-filled, fossil foraminifera are abun- dant and were eroded from sedimentary units and transported by fluvial or wave activity to Sendai Bay. Trends associated with test size (e.g. decreasing concentration of large test sizes with distance inland) are in agreement with grain size data. At two locations a decrease in total organic carbon and an increase in δ13C were found in the tsunami sand compared with the underlying soil, supporting a beach to intertidal or- igin for the upper unit. © 2012 Elsevier B.V. All rights reserved. 1. Introduction the Pacific northwest (Kelsey et al., 2005), North Sea (Bondevik et al., 2005), New Zealand (Goff et al., 2001), Kamchatka (Pinegina Records of past tsunamis developed from the sedimentary evi- et al., 2003) and the South Pacific(Goff et al., 2011), and in the dence they leave behind, improve our understanding of the frequency regions affected by the 1960 Chile (Cisternas et al., 2005) and 2004 of tsunamis by expanding the age range of events available for study Indian Ocean (e.g. Jankaew et al., 2008) earthquakes. (Morton et al., 2007). Proper hazard assessment depends on an The identification of tsunami deposits is often based on the recogni- awareness of tsunamis and their impacts on coastal geomorphology, tion of anomalous sand units in low-energy environments such as ecology and rapidly expanding coastal populations. Stratigraphical coastal ponds, lakes, and marshes, which can be supported by microfos- sequences of tsunami deposits are often used to estimate recurrence sil evidence. For example, the A.D. 1700 Cascadia tsunami can be iden- intervals and provide insight into their source (e.g. earthquakes, tified with confidence from a sand unit that tapers landward (often landslides, volcanic eruptions; Bernard and Robinson, 2009). Recon- for several kilometers), contains a mixed microfossil assemblage and structions have shown repeated tsunamis during the Holocene in coincides with stratigraphical evidence for abrupt coseimic subsidence (e.g. Hemphill-Haley, 1995; Hawkes et al., 2011). Foraminiferal taxono- my has been commonly used as an indicator of tsunami deposits (e.g. ⁎ Corresponding author at: Sea Level Research, Department of Earth and Environmental Mamo et al., 2009) and most taphonomic studies of foraminifera focus Science, University of Pennsylvania, 240 S. 33rd Street, Philadelphia, PA 19104‐6316, USA. Tel.: +1 215 573 5145. on time-averaging or lateral transport of tests with only semi- E-mail address: [email protected] (J.E. Pilarczyk). quantitative observations on test condition (e.g. Hawkes et al., 2007; 0037-0738/$ – see front matter © 2012 Elsevier B.V. All rights reserved. http://dx.doi.org/10.1016/j.sedgeo.2012.08.011 J.E. Pilarczyk et al. / Sedimentary Geology 282 (2012) 78–89 79 Kortekaas and Dawson, 2007; Uchida et al., 2010). Recent research has have not been studied. The tsunami sand deposit extended 2.8 km in- shown that test condition provides further information regarding ener- land, however, since the Sendai plain coastline has prograded 1 km gy regimes and transport history (e.g. Hawkes et al., 2007; Kortekaas over the last ~1000 years, the inland extent of the Jōgan sand deposit and Dawson, 2007; Uchida et al., 2010; Pilarczyk et al., 2011; Pilarczyk is now ~4 km inland (Sawai et al., 2008b; Sugawara et al., 2011b). and Reinhardt, 2012a, 2012b). The proxy toolkit to examine paleo-tsunamis has expanded fol- 2. Regional setting lowing the modern surveys on the 2004 Indian Ocean and 2009 South Pacific tsunamis (Chagué-Goff et al., 2011). While geochemis- The Sendai plain is a low-lying (less than 5 m above TP; Tokyo Peil; try has been used for more than two decades to provide evidence mean sea level in Tokyo Bay), wave-dominated, microtidal (mean tidal for marine inundation in paleo-tsunami studies (e.g. Minoura and range of ~1 m) coastal plain, which extends approximately 50 km on Nakaya, 1991; Minoura et al., 1994; Goff and Chagué-Goff, 1999; the Pacific coast of north-eastern Japan (Fig. 1a). The area is bounded Chagué-Goff et al., 2002; Chagué-Goff, 2010), it has also recently by hills to the north, west and south, and a steep continental shelf gra- been used in studies of modern tsunamis (e.g. Chagué-Goff et dient (Tamura and Masuda, 2004, 2005). Early Miocene to Holocene al., 2011; Chagué-Goff et al., 2012–this issue). In this study we de- marine and non-marine sediments dominate the coastal plain with scribe foraminiferal assemblages (taxa and taphonomic), general Middle Jurassic to Early Cretaceous marine sedimentary rock outcrop- sedimentology (grain size) and geochemistry (TOC and δ13C) as ping to the north at Oshika Peninsula, as well as to the south near indicators of the 11th March 2011 Tōhoku-oki tsunami deposit. Sōma (Fig. 1b; Geological Survey of Japan, 2009). The area is character- Foraminifera and sedimentological data from a trench containing ized by a series of prograding Late Holocene beach ridges and freshwa- the A.D. 869 Jōgan tsunami deposit are also presented. Readers are re- ter back marshes. Sugawara et al. (2012) describe several artificial ferred to Szczuciński et al. (2012–this volume) for a detailed analysis geomorphic features (e.g. breakwaters, coastal forest, Teizan canal, irri- of the sedimentological and microfossil variability within the gation channels, etc.) that likely affected the run-up associated with the Tōhoku-oki tsunami deposit along the transect. Tōhoku-oki tsunami but were not in place in Jōgan time. Freshwater marshes along the Sendai plain support rice cultivation, with many 1.1. 2011 Tōhoku-oki tsunami fields interspersed with low-density housing (Fig. 1c). Main sediment sources to the area include three rivers (the Abukuma, Natori and On 11th March 2011 a great megathrust earthquake (Mw 9.0) Nanakita rivers) that account for much of the continued seaward along the Japan Trench generated a tsunami that reached the Sendai progradation of the coastline since the Middle Holocene (Saito, 1991; plain on the northeastern coast of Honshu, Japan (Fig. 1a) at 14:46 Tamura and Masuda, 2005). (Japan Standard Time) with run-up heights of 10–40 m (Mori et al., The study area (near Sendai airport) consists of four key environ- 2011). The earthquake ruptured over a distance of ~400 km with up- ments: coastal; coastal forest; paved landscape; and rice fields. The wards of 5‐m vertical and 24 to 60‐m lateral displacement of the sea- coastal zone transitions from intertidal marine (0.8 m below TP) to floor (Ito et al., 2011; Sato et al., 2011). The low-lying configuration of beach (1.7 m above TP) to artificial dune (2.3 m above TP; Figs. 1c, the coastal plain made Sendai particularly susceptible to tsunami in- 2, and 3a) within a distance of ~0.50 km from the shoreline. The arti- undation that reached 4.8 km inland (Association of Japanese ficial dune is composed of allochthonous sediment that was brought Geographers, 2011; Chagué-Goff et al., 2012–this issue), and in to armor the coastline (Fig. 2a). We do not know the origin of the sustained flooding several months after the event was documented dune sediment, but note that it consists of a core of loose gray sand at several locations (Sugawara et al., 2011a; Chagué-Goff et al., overlain by a ~0.3‐m layer of compacted, yellow-brown sand with a 2012–this issue).
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